A coastal zone is the interface between the land and water. These
zones are important because a majority of the world's population inhabit such zones.
Coastal zones are continually changing because of the dynamic interaction between the
oceans and the land. Waves and winds along the coast are both eroding rock and
depositing sediment on a continuous basis, and rates of erosion and deposition vary
considerably from day to day along such zones. The energy reaching the coast can
become high during storms, and such high energies make coastal zones areas of high
vulnerability to natural hazards. Thus, an understanding of the interactions of the
oceans and the land is essential in understanding the hazards associated with coastal
zones. Tides, currents, and waves bring energy to the coast, and thus we start
with these three factors.

Tides

Tides are due to the gravitational attraction of Moon and to
a lesser extent, the Sun on the Earth. Because the Moon is closer to the Earth than the
Sun, it has a larger affect and causes the Earth to bulge toward the moon.

At the same time, a bulge occurs on the opposite side of the Earth due to inertial
forces the explanation is beyond the scope of
this course). These bulges remain stationary while Earth rotates.

The tidal bulges result in a rhythmic rise and fall of ocean surface, which is not
noticeable to someone on a boat at sea, but is magnified along the coasts. Usually there
are two high tides and two low tides each day, and thus a variation in sea level as the
tidal bulge passes through each point on the Earth's surface.

Along most coasts the range is about 2 m, but in narrow inlets tidal currents can be
strong and fast and cause variations in sea level up to 16 m.

The highest high tides occur Because the Sun also exerts a gravitational attraction on the Earth,
there are also monthly tidal cycles that are controlled by the relative position of the
Sun and Moon. when the Sun and the Moon are on the same side
of the Earth (new Moon) or on opposite sides of the Earth (full Moon). The lowest high
tides occur when the Sun and the Moon are not opposed relative to the Earth (quarter
Moons).

These highest high tides become important to coastal areas during hurricane season and
you always hear dire predications of what might happen if the storm surge created by the
tropical cyclone arrives at the same time as the highest high tides.

Fluctuations in Water Level

While sea level fluctuates on a daily basis because of the tides, long term
changes in sea level also occur. Such sea level changes can be the result of local
effects such as uplift or subsidence along a coast line. But, global changes in sea
level can also occur. Such global sea level changes are called eustatic changes. Eustatic sea level changes are the result of either changing the volume of
water in the oceans or changing the shape of the oceans. For example, during
glacial periods much of the water evaporated from the oceans is stored on the continents
as glacial ice. This causes sea level to become lower. As the ice melts at the
end of a glacial period, the water flows back into the oceans and sea level rises.
Thus, the volume of ice on the continents is a major factor in controlling eustatic
sea level. Global warming, for example could reduce the amount of ice stored on the
continents, thus cause sea level to rise. Since water also expands (increases its
volume) when it is heated, global warming could also cause thermal expansion of sea water
resulting in a rise in eustatic sea level. Changing the shape of the oceans occurs if volcanic output on the sea floor or at oceanic ridges increases substantially, thus raising the floor of the oceans.

Oceanic Currents

Oceanic circulation is three dimensional. Most visible to humans are the surface ocean currents that are mainly driven by the wind. Vertical currents and deep ocean currents are driven by upwelling and downwelling near the coasts and differences in density, temperature and salinity between the surface waters and the deep ocean waters.

The surface of the oceans move in response to
winds blowing over the surface. The winds, in effect, drag the surface of oceans
creating a current of water that is usually no more than about 50 meters deep. Thus,
surface ocean currents tend to flow in patterns similar to the winds as discussed previously,
and are reinforced by the Coriolis Effect. But, unlike winds, the ocean currents are
diverted when they encounter a continental land mass.

The surface currents have the following properties:

Because of the Coriolis effect, circulation is clockwise in the northern hemisphere and counterclockwise in the southern hemisphere.

In each hemisphere cooler waters from higher latitudes circulate toward the equator where they are warmed and circulate back toward the poles.

As surface waters approach the coast, they have to push the water down in order to make room for more water to come in.
This results in downwelling currents. If surface waters move away from the coast, water from below rises to replace the water removed, resulting in upwelling.

In the middle latitudes ocean currents run generally eastward, flowing clockwise in
the northern hemisphere and counterclockwise in the southern hemisphere. Such
easterly flowing currents are deflected by the continents and thus flow circulates back
toward the west at higher latitudes. Because of this deflection, most of the flow of
water occurs generally parallel to the coasts along the margins of continents. Only
in the southern oceans, between South America, Africa, Australia, and Antarctica are these
surface currents unimpeded by continents, so the flow is generally in an easterly
direction around the continent of Antarctica.

Seawater also circulates vertically as a result of changes in density controlled by changing salinity and temperature. Because it controlled by both temperature and salinity differences, is called thermohaline circulation.

Ocean Waves

Waves are generated by winds that blow over the surface of
oceans. In a wave, water travels in loops. But since the surface is the area affected, the
diameter of the loops decreases with depth. The diameters of loops at the surface is equal
to wave height (h).

Wave Base - Motion of waves is only effective at moving water
to depth equal to one half of the Wavelength (L/2). Water deeper than L/2 does not move.
Thus, waves cannot erode the bottom or move sediment in water deeper than L/2. This depth
is called wave base. In the Pacific Ocean, wavelengths up to 600 m have been observed,
thus water deeper than 300m will not feel passage of wave. But outer parts of continental
shelves average 200 m depth, so considerable erosion can take place out to the edge of the
continental shelf with such long wavelength waves.

When waves approach shore, the water depth decreases and the wave will start feeling
bottom. Because of friction, the wave velocity (= L/P) decreases, but its period (P)
remains the same Thus, the wavelength (L) will decrease. Furthermore, as the wave
"feels the bottom", the circular loops of water motion change to elliptical
shapes, as loops are deformed by the bottom. As the wavelength (L) shortens, the wave
height (h) increases. Eventually the steep front portion of wave cannot support the water
as the rear part moves over, and the wave breaks. This results in turbulent water of the
surf, where incoming waves meet back flowing water. Waves that crash onto the beach are called breakers. Wave energy is dissipated by turbulence, which creates frothy white water in the surf zone. A surge of water (swash) rushes up the beach face.
Gravity pulls the backwash down the slope of the beach.

Rip currents form where water is channeled back into ocean.

Wave refraction - Waves generally do not approach shoreline parallel to shore.
Instead some parts of waves feel the bottom before other parts, resulting in wave
refraction or bending.

Wave energy can thus be concentrated on headlands, to form cliffs. Headlands erode
faster than bays because the wave energy gets concentrated at headlands.

Coastal Erosion and Sediment Transport

Coastlines are zones along which water is continually making
hanges. Waves can both erode rock and deposit sediment. Because of the continuous
nature of ocean currents and waves, energy is constantly being expended along coastlines
and they are thus dynamically changing systems, even over short (human) time scales.

Erosion by Waves

As we discussed previously, the motion of waves is only felt to a depth of 1/2 times
the wavelength. Thus, waves can only erode if the water along a coastline is
shallower than 1/2 times the wavelength. But, when the wave breaks as it approaches
the shoreline, vigorous erosion is possible due to the sudden release of energy as the
wave flings itself onto the shore. Rigorous erosion of sea floor takes place in the surf zone, i.e.
between shoreline and breakers. Waves break at depths between 1 and 1.5 times wave height.
Thus for 6 m tall waves, rigorous erosion of sea floor can take place in up to 9 m of
water. In the breaker zone rock particles carried in
suspension by the waves are hurled at other rock particles. As these particles
collide, they are abraded and reduced in size. Smaller particles are carried more
easily by the waves, and thus the depth to the bottom is increased as these smaller
particles are carried away by the retreating surf. Furthermore, waves can undercut
rocky coastlines resulting in mass wasting processes wherein material slides, falls,
slumps, or flows into the water to be carried away by further wave action.

Transport of Sediment by Waves and Currents

Sediment that is created by the abrasive action of the waves or sediment brought to the
shoreline by streams is then picked up by the waves and transported. The finer
grained sedimentis carried offshore to be deposited on the continental shelf or in
offshore bars, the coarser grained sediment can be transported by longshore currents and
beach drift.

Longshore currents - Most waves arrive at the shoreline at an angle, even
after refraction. Such waves have a velocity oriented in the direction perpendicular to
the wave crests, but this velocity can be resolved into a component perpendicular to the
shore (Vp) and a component parallel to the shore (VL). The component parallel
to the shore can move sediment and is called the longshore current.

Beach drift - is due to waves approaching at angles to beach, but
retreating perpendicular to the shore line. This results in the swash of the incoming wave
moving the sand up the beach in a direction perpendicular to the incoming wave crests and
the backwash moving the sand down the beach perpendicular to the shoreline. Thus, with
successive waves, the sand will move along a zigzag path along the beach.

Coastal Processes

Coastlines represent a balance between wave energy and sediment supply.

If wave energy and sediment supply are constant, then a steady state is reached. If any one of these factors change, then shoreline will adjust.

Due to input of sediment from rivers, marine deltas may form, due to beach and longshore drift such features as spits, tombolos, and bay barriers may form

Types of Coasts

The character and shape of coasts depends on such factors as tectonic activity, the
ease of erosion of the rocks making up the coast, the input of sediments from rivers, the
effects of eustatic changes in sea level, and the length of time these processes have been
operating.

Rocky Coasts - In general, coastlines that have experienced recent tectonic uplift as a
result of either active tectonic processes (such as the west coast of the United States)
or isostatic adjustment after melting of glacial ice (such as the northern part of the
east coast of the United States) form rocky coasts with cliffs along the shoreline.
Anywhere wave action has not had time to lower the coastline to sea level, a rocky coast
may occur. .

Because of the resistance to erosion, a wave cut bench and wave cut cliff
develops. The cliff may retreat by undercutting and resulting mass-wasting processes. If subsequent uplift of the wave-cut bench occurs, it may be preserved above sea level
as a marine terrace.

In areas where differential erosion takes place, the undercutting may initially produces sea caves. If sea caves from opposite sides of a rocky headland meet, then a sea arch may form. Eventual weakening of the sea arch may result in its collapse to form a sea stack.

Because cliffed shorelines are continually attacked by the erosive and undercutting
action of waves, they are susceptible to frequent mass-movement processes which make the
tops of these cliffs unstable areas for construction as you noted in your homework on
mass movement processes.

Along coasts where streams entering the ocean have cut through the rocky cliffs, wave
action is concentrated on the rocky headlands as a result of wave refraction, as discussed
previously.

Beaches - A beach is the wave washed sediment along a coast.
Beaches occur where sand is deposited along the shoreline. A beach can be divided into a
foreshore zone, which is equivalent to the swash zone, and backshore zone, which is
commonly separated from the foreshore by a distinct ridge, called a berm. Behind the
backshore may be a zone of cliffs, marshes, or sand dunes.

Barrier Islands - A barrier island is a long narrow ridge of sand just
offshore running parallel to the coast. Separating the island and coast is a narrow
channel of water called a lagoon. Most barrier islands were built during after the last
glaciation as a result of sea level rise. Barrier islands are constantly changing. They
grow parallel to the coast by beach drift and longshore drift, and they are eroded by
storm surges that often cut them into smaller islands. Barrier islands are common
along the east and Gulf coasts of the United States.

Reefs and Atolls - Reefs consist of colonies of organisms, like corals,
which secrete calcium carbonate. Since these organisms can only live in warm waters and
need sunlight to survive, reefs only form in shallow tropical seas. Fringing reefs form
along coastlines close to the sea shore, whereas barrier reefs form offshore, separated
from the land by a lagoon. Both types of reefs form shallow water and thus protect
the coastline from waves. However, reefs are high susceptible to human activity and
the high energy waves of storms.

In the deeper oceans reefs can build up on the margins of volcanic islands, but only do so after the volcanoes have become extinct.
After the volcanism ceases, the volcanic island begins to erode and also begins to subside.As the island subsides, the reefs continue to grow upward. Eventually, the original volcanic island subsides and is eroded below sea level. But, the reefs trap sediment and a circular or annular island, called an atoll, forms.

Estuaries- Coastal river valleys flooded by sea water are called estuaries.
They are chracterized by mixing of fresh and salt water.
Most modern estuaries are related to sea level rise since the last glaciation.

Tidal Flats - These are zones along the coast that are flooded during hight tides and form in the intertidal zones lacking strong waves.
They are common behind barrier islands or in estuaries.

Coastal Variability

The shape of coast is controlled mainly by tectonic forces and climate, both of which act to determine the elevation of the coast.
Plate tectonic setting governs the style of coastline.In general, along passive margins where not tectonic activity is currently taking place, broad low lying coastal plains dominate.

Along active margins, uplifted rocky coasts dominate.

Emergent coasts result from local tectonic or uplift or from a drop in eustatic sea level.
Emergent coasts are characterized by rocky coasts with sea cliffs and raised wave cut benches (marine terraces). The west coast of the U.S. is a rugged emergent coast with many sea cliffs and raised wave cut
benches (marine terraces). In this case is due to a recent episode of uplift of the land relative to the sea by
tectonic forces. The coast of New England is also an emergent case, but in this case, the
rise of the land surface has been due to removal of glacial ice which had depressed the
land during the last glaciation which ended about 10,000 years ago.

Submergent coasts result from either subsidence along the coast due to tectonic forces or eustatic sea level rise.
These are characterized by gentle shorelines, flooded river valleys (estuaries and fjords), and barrier islands. Much of the East Coast and Gulf Coast of the U.S. has these characteristics which are attributed to the rise of eustatic sea level since last glaciation.

Coastal Hazards

Sea Level Rise - Sea level is presently rising and the rate of sea level rise may increase due to melting of continental ice sheets like now cover Greenland and Antarctica. Human habitation of low-lying coastlines may be in jeopardy in the near future. Higher sea level will make these coastal areas more susceptible to other hazards, like storms and tsunami.

Storms - great storms such as hurricanes or other winter storms can cause erosion of the
coastline at much higher rate than normal. During such storms beaches can erode rapidly
and heavy wave action can cause rapid undercutting and mass-wasting events of cliffs along
the coast, as noted above. Note that the El Niņo driven storms on the west coast
caused extensive coastal erosion in 1998.

High winds blowing over the surface of the water during storms bring
more energy to the coastline and can cause more rapid rates of erosion. Erosion
rates are higher because:

During storms wave velocities are higher and thus larger particles can be carried in
suspension. This causes sand on beaches to be picked up and moved offshore, leaving
behind coarser grained particles like pebbles and cobbles, and reducing the width of the
beach.

During storms waves reach higher levels onto the shoreline and can thus remove
structures and sediment from areas not normally reached by the incoming waves.

As the waves crash into rocks, air occupying fractures in the rock becomes compressed
and thus the air pressure in the fractures is increased. Such pressure increases can
cause further fracture of the rock.

As we have seen in our discussion of tropical cyclones, wind driven storm surge and can flood coastal areas and cause much death and destruction.

Tsunami - a tsunami is a giant sea wave generated by earthquakes,
volcanic eruptions, or landslides, as we have discussed before. Such waves can have
wave heights up to 30 m, and have great potential to wipe out coastal cities.

Landslides - On coasts with cliffs, the main erosive force of the waves is concentrated
at the base of the cliffs. As the waves undercut the cliffs, they may become unstable and
mass-wasting processes like landslides or rockfalls will result. Massive landslides can also generate
tsunami.

Mitigating Against Coastal Hazards

Shoreline protection
can be divided into two categories: hard stabilization in which structures are built to
reduce the action of the waves and soft stabilization which mainly refers to adding
sediment back to a beach as it erodes away.

Hard Stabilization

Seacliffs, since they are susceptible to landslides due to undercutting, and barrier
islands and beaches, since they are made of unconsolidated sand and gravel, are difficult
to protect from the action of the waves. Human construction can attempt to prevent
erosion, but cannot always protect against abnormal conditions.

Two types of hard stabilization are often used.

One type interrupts the force of the waves. Seawalls are built
parallel to the coastline to protect structures on the beach. A seawall is usually
built of concrete or piles of large rocks. Waves crash against the seawall and are
prevented from running up the beach. Breakwaters serve a similar purpose, but are
built slightly offshore, again preventing the force of the waves from reaching the beach
and any structures built on the beach.

The other type interrupts the flow of sediment along the beach.
These structures include groins and jetties, built at right angles to the beach to
trap sand and widen the beach.

While hard stabilization does usually work for its intended purpose, it does cause
sediment to be redistributed along the shoreline. Breakwaters, for example cause
wave refraction, and alters the flow of the longshore current. Sediment is trapped
by the breakwater, and the waves become focused on another part of the beach, not
protected by the breakwater, where they can cause significant erosion. Similarly, because
groins and jetties trap sediment, areas in the downdrift direction are not resupplied with
sediment, and beaches become narrower in the downdrift direction.

Soft stabilization is primarily accomplished by adding sediment to the coastline,
usually by dredging sediment from offshore and pumping it onto the coastline. Adding
sediment is necessary when erosion removes too much sediment. But, because the
erosive forces are still operating, such addition of sediment will need to be periodically
repeated.

Coastal Protection Controversies

As noted above, hard stabilization
usually affects areas in the downdrift direction of the longshore current. The net
result being that some areas of a coastline are protected while other areas are
destroyed. Nearly all human intervention with coastal processes interrupts natural
processes and thus can have an adverse effect on coastlines. Three examples of human
interference are discussed below.

Barrier Islands along the North Carolina Coast show a noticeable difference among the
islands that have been built upon and those that have not. The undeveloped islands
have beaches 100 to 200 meters wide, while the developed islands have beaches with widths
less than 30 m.

In order to protect southern California cities from flooding caused by heavy rains, most
of the streams draining into the ocean have been dammed. The dams trap sediment that
would normally be carried to the ocean by stream flow. Since this sediment is not
being supplied to the ocean, longshore currents cannot resupply the beaches with sediment,
but do carry the existing sediment in the downdrift direction, resulting in significant
erosion of the beaches.

Most of the state of Louisiana has resulted from the deposition of sediments by the
Mississippi River during floods over the last 10,000 years. Humans, however, have
prevented the River from flooding by building a levee systems that extends to the mouth of
the River. As previously deposited sediments become compacted they tend to
subside. But, since no new sediment is being supplied by Mississippi River flooding,
the subsidence results in a relative rise in sea level. This, coupled with a
current rise in eustatic sea level, is causing coastal Louisiana to erode at an incredible
rate, estimated at 25 square miles a year (equivalent to the area one football field disappearing every 45 minutes). An excellent series of
articles concerning the coastal erosion problem in Louisiana was publishedrecently by the Times-Picayune newspaper. See the article and
the accompanying flash animation at:

Many have suggested that the best way to adjust to coastal erosion is to leave the
coastlines alone. This, of course will not solve the problems of southern California
or Louisiana, because both areas need the flood protection measures. Nevertheless, in
some coastal areas zoning laws have been enacted to prevent development along beaches, and
in other areas building codes are enforced to protect the natural environment.